74 o 52'30" 40 o 45' 50' 47'30" 74 o 45' 40 o 45' A A' B B' 42'30" 40' 40 o 37'30" 74 o 45' 47'30" 50' 74 o 52'30" 40 o 37'30" 40' 42'30" HACKETTSTOWN GLADSTONE FLEMINGTON HIGH BRIDGE Geology mapped 1988, 2015 Cartography by S. Stanford Base map from U. S. Geological Survey, 1954. Photorevised 1970. Corner ticks are on North American Datum of 1927. Research supported by the U. S. Geological Survey, National Cooperative Geologic Mapping Program, under USGS award number G14AC00238. The views and conclusions contained in this document are those of the author and should not be interpreted as necessarily representing the official policies, either expressed or implied, of the U. S. Government. . . . . . . . . . . . . . . . . . .. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! !! ! ! ! ! ! ! ! ! ! !! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! !!! ! ! ! ! ! ! ! ! ! !! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! !! ! ! ! ! ! ! ! ! ! !! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! !! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! !! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! !! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! !! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! Qcg Qwgt Qwgt Qcg Qcal Qwg Qwg Qwgt Qcg Qcg Qwgt Qcg Qwg Qcg Qwgt Qwgt Qcal Qcal Qaf Qpt Qwg Qwgt Qcg Qwgt Qwg Qcg Qwcb Qwcb Qwg Qal Qal Qtl Qwcb Qpt Qtl Qtl Qcg Qccb Qwgt Qwg Qwgt Qal Qaf Qaf Qcal Qcal Qcal Qtl Qcg Qwgt Qwgt Qcal Qal Qwcb Qcg Qwg Qwgt Qcg Qcal Qwgt Qcg Qwgt Qwg Qwg Qcal Qcg Qcg Qwg Qwg Qcg Qcal Qcg Qwgt Qcal Qcal Qcg Qwg Qcal Qwg Qwgt Qwg Qcal Qwgt Qwg Qcal Qcg Qwg Qwg Qwg Qcal Qwgt Qwgt Qwgt Qcg Qcal Qwgt Qcg Qwg Qwg Qcg Qcg Qcal Qcg Qwg Qwg Qpt Qcg Qcal Qwg Qcg Qwgt Qcg Qwg Qwg Qcal Qcg Qcal Qcg Qcg Qcg Qcg Qwg Qcg Qaf Qcg Qwgt Qtl Qtl Qwcb Qpt Qwcbt Qwcbt Qwg Qcg Qaf Qal Qwgt Qcg Qwgt r r r r Qcg Qwg Qwg Qwgt Qwgt Qcg Qwg Qcal Qwgt Qcal Qaf Qcg Qwg Qwgt r r r r r r r r r Qwgt Qwgt Qwgt Qcg Qcg Qcal Qcg Qwg Qwg Qwgt r Qwgt Qcal Qcg Qcg Qcg Qcg Qwgt Qcg Qcg Qwgt Qwg Qcg Qcg Qwgt Qcal Qcg Qcg Qcg Qwgt Qcal Qcal Qwgt Qcg Qcg Qcg Qcal Qwgt r Qwgt Qwgt Qwg Qwg Qcg Qwg Qcg Qcg Qwgt Qwgt Qcg Qwgt Qcg Qcg Qwgt Qcal Qcg Qcg Qcg Qcg Qwgt Qcal Qcg Qwg Qwgt Qcg Qcg Qcg Qal Qcal Qwgt Qwg Qcal Qwg Qcg Qcg Qwg Qwg Qcg Qcal r Qcal r r r Qwgt Qwgt Qwg Qwgt Qwgt Qcg Qwgt Qcg Qaf Qcg Qcg Qcal Qcg Qaf Qaf Qal Qws Qcg Qpt Qpt Qwc Qwb Qcb Qcb Qwb Qws Qpt Qws Qcb Qwb Qpt Qal Qwg Qcg Qcal Qal Qaf Qaf Qcal Qtl Qwc Qcal Qcal Qws Qtl Qal Qpt Qcg Qcal Qwg Qwgt Qcal Qcg Qwg Qwg Qwg Qws Qwg Qcg Qwg Qcal Qwgt Qcg Qcg Qcal Qwg Qcg Qtl Qtl Qcal Qcal Qcal Qwgt Qwg Qcal Qwg Qpt Qwg Qal Qwg Qcg Qpt Qwg Qwgt Qwg Qps Qps Qcg Qcg Qwgt Qcal Qaf Qal Qpt Qwg Qcg Qwgt Qcg Qcg Qcal Qaf Qwg Qwc Qaf Qwc Qtl Qtl Qws Qws Qpt Qwc Qws Qcg Qcal Qcg Qwc Qcg Qwgt Qwgt Qcal Qtl Qpt Qwc Qwc Qpt Qpt Qpt Qpt Qwb Qcs Qws Qps Qws Qcb Qws Qws Qwc Qcal Qal Qcal Qtu Qtu Qws Qtu Qtu Qws Qtl Qws Qcal Qwc Qws Qtl Qcb Qcb Qws Qtl Qtl Qtl Qpt Qtl Qws Qal Qtl Qtl Qws Qpt Qpt Qws Qws Qtu Qal Qcal Qtuo Qtuo Qtu Qcs Qws r Qcal Qtu Qal Qpt Qws Qtu Qws Qtu r Qtu Qws Qpt Qps Qtu Qal Qcd Qcd Qws Qwd Qwdt Qcd Qws Qtl Qtl Qtl Qtl Qtu Qwd r r r Qwd Qcd Qcd Qws Qwd Qps Qwc Qal Qws Qws Qws r Qcg Qwg Qws Qwdt Qcal Qwg Qcg Qcal Qwg Qcg Qcal Qwg Qwcb Qpt Qwcb Qal Qpt Qpt Qal Qal 3 1 2 4 5 6 7 8 9 10 11 12 13 14 15 148 149 17 16 18 19 20 22 23 21 27 26 28 24 25 29 30 31 147 32 r 34 33 41 35 36 143 144 145 146 497 498 499 500 501 502 503 177 181 182 141 140 138 139 184 192 132 137 194 134 135 197 196 133 131 130 129 128 127 126 125 123 124 121 120 118 117 119 114 113 112 116 115 122 42 38 37 43 40 39 44 55 54 45 46 47 53 50 49 52 51 48 56 496 102 103 99 98 97 66 65 57 58 59 60 61 101 100 104 107 106 105 108 111 109 110 62 68 69 63 64 77 67 78 76 70 71 72 73 74 75 79 80 81 82 83 84 87 88 89 90 91 92 93 202 136 94 95 96 203 201 205 206 207 208 209 210 211 213 314 317 212 320 319 318 315 316 313 312 311 214 215 216 200 199 198 195 193 290 289 217 218 219 220 221 222 223 190 191 189 188 187 185 186 183 179 180 178 176 175 458 174 173 172 224 225 228 229 230 226 265 266 267 268 269 227 231 232 233 234 150 151 152 153 154 155 157 158 159 156 160 161 163 164 165 162 166 167 168 169 170 171 457 238 236 237 235 240 247 239 241 242 243 244 245 246 397 398 396 395 385 386 387 408 407 406 414 410 411 412 413 405 388 389 384 254 253 383 380 379 382 381 378 376 375 377 248 249 250 251 252 255 256 257 258 259 260 261 263 262 369 368 367 366 365 370 264 272 271 274 273 282 Qwgt 284 283 281 280 279 278 275 277 276 Qwgt 364 362 360 359 285 286 287 Qwg 293 294 295 299 300 296 297 298 302 301 306 305 307 303 304 325 459 310 309 308 495 324 323 322 326 327 328 330 329 331 332 333 334 328 329 335 337 336 340 341 342 343 344 346 345 444 445 446 447 448 449 450 451 351 349 347 460 348 350 354 355 358 357 356 361 419 353 420 358 421 422 423 424 427 428 426 425 86 440 439 438 437 436 433 435 429 430 431 432 434 441 442 443 371 418 417 373 372 374 391 392 390 393 394 400 401 399 403 402 404 416 415 453 482 463 485 486 488 487 489 484 467 493 465 464 455 456 454 466 462 492 490 491 494 468 483 481 480 479 475 476 477 478 469 470 471 472 473 474 452 Qcg 85 409 Qcg 292 291 288 321 Qcal Qtu Qal Qwg 204 363 figure 4 figure 3 figure 5 270 Qcal Qal Qal Qaf Qcal Qps Qcb Qcd Qwb Qws Qpt CORRELATION OF MAP UNITS Holocene late Pleistocene middle Pleistocene early Pleistocene Wisconsinan Illinoian pre-Illinoian NORTH AMERICAN GLACIAL STAGE EPOCH AND AGE Qcs Qcg Qwg Qwc Qwcb Qwd Qtu Qtl stream incision stream incision stream incision, extensive erosion weathered-rock materials colluvium fluvial, glacial, and man-made deposits Sangamonian Pliocene Qccb stream incision Qtuo Qwdt Qwgt Qwcbt 1100 1000 900 800 700 600 500 400 300 200 VERTICAL EXAGGERATION 10X ELEVATION (feet) Qwg Qcal 1 2 Qcg Qcal Qwg Qwg SLIKER ROAD COUNTY ROUTE 513 Qwg Qcg Qpt Qwcb Qwg Qcg Qal 497 500 Qwcb Qwg Qcal Qwg 127 Qwg Qcg 183 186 185 Qcg Qcal 187 188 Qwg Qcal 195 Qpt Qwg Qcal SOUTH BRANCH RARITAN RIVER FOX HILL FARMERSVILLE ROAD ROCKAWAY CREEK Qwg COUNTY ROUTE 517 COUNTY ROUTE 512 Qal Qwg Qcal Qwg 201 202 95 96 1100 1000 900 800 700 600 500 400 300 200 A' A Bedrock Bedrock BEND IN SECTION 500 400 300 200 100 0 ELEVATION (feet) B Qwg Qal Qpt Qwg BEAVER BROOK PETTICOAT LANE VERTICAL EXAGGERATION 10X 453 INTERSTATE ROUTE 78 Qps Qal Qpt Qws Qal Qpt Qws COKESBURY ROAD BLOSSOM HILL ROAD DEER HILL ROAD Qtl Qal Qtl Qwc Qpt Qal Qpt Qwc Qal 423 422 421 429 435 445 449 448 Qpt Qws Qwb Qps Qws Qal Qws Qal Qtl Qcb excavated POTTERSTOWN ROAD ROCKAWAY CREEK Qwb Qcb Qpt Qws Qwb Qws 500 400 300 200 100 0 B' Qpt Qwc BEND IN SECTION Lebanon Potterstown McCrea Mills Oldwick Cokesbury Fairmount Farmersville Little Brook Califon LONG VALLEY FOX HILL RANGE HELL MOUNTAIN ROUND TOP CUSHETUNK MOUNTAIN Califon Quadrangle Flemington Quadrangle HIGHLAND ESCARPMENT M1 M1 M1 M2 M3 M4 Rockaway Creek South Branch Rockaway Creek Rockaway Creek Round Valley Reservoir South Branch Raritan River Bissell 0 1 mile late Miocene land surface early Pleistocene-Pliocene land surface pre-Illinoian glacial lake pre-Illinoian glacier margin limit of early and middle Pleistocene valley incision pre-Illinoian lake drainage Figure 1.--Geomorphic and glacial features of the Califon quadrangle and part of the Flemington quadrangle. Abbreviations are: M1=limit of pre-Illinoian glacier. Glacial lake ponded against Cushetunk Mountain. M2=ice margin during deposition of high gravels at Lebanon. Glacial lakes ponded against upland to west. M3=ice margin during deposition of low gravels at Lebanon. Glacial lake ponded in north-draining valley in Round Valley. M4=ice margin during deposition of gravels at McCrea Mills. Lake ponded in north-draining valley south of Bissell. ? ? ? GRANITE GNEISS GNEISS GNEISS GNEISS GRANITE GRANITE GRANITE GRANITE GRANITE GNEISS GRANITE GNEISS GNEISS GNEISS CARBONATE GNEISS CONGLOMERATE BASALT BA SHALE SHALE DIABASE GNEISS GRANITE SHALE CARBONATE GRANITE GRANITE CONGLOMERATE GNEISS GNEISS South Rockaway Branch Creek Rockaway Creek Beaver Brook South Branch Raritan River Rockaway Creek bedrock outcrop area <25 feet 25-50 feet 50-100 feet >100 feet well or boring (anomalous thicknesses queried) isolated bedrock outcrop bedrock contact 0 1 mile Figure 2.--Thickness of surficial material, including weathered rock, and bedrock lithologies in the Califon quadrangle. "Gneiss" includes metasedimentary and metavolcanic gneiss, "granite" includes gneissic granite and related intrusive rocks. Abbreviation "BA" indicates basalt. Note thick weathered carbonate rock adjacent to gneiss uplands, and thick weathered carbonate-clast conglomerate in the Newark Basin. Bedrock contacts simplified from Volkert (1989, unpublished). Little Brook Califon Farmersville Fairmount Oldwick McCrea Mills Bissell Cokesbury Lebanon Potterstown INTRODUCTION The Califon quadrangle is located in northwestern New Jersey, on the border of the Highlands and Newark Basin geologic provinces. The Highlands province, which covers the northwestern two-thirds of the quadrangle, is an upland formed on gneiss and granite of Middle Proterozoic age. It includes two low-lying inliers of Paleozoic carbonate rock: one in Long Valley, the other in the southwestern corner of the quadrangle. The Newark Basin, which covers the southeastern third of the quadrangle, is a half-graben of Triassic and Jurassic age containing shale, conglomerate, basalt, and diabase. Shale and conglomerate underlie the broad lowland developed on the Newark Basin rocks. Within this lowland, ridges are formed on basalt and diabase. Basalt underlies Round Top and the arcuate ridge at McCrea Mills. Diabase underlies Cushetunk Mountain. A prominent 500-foot tall scarp, the Highland escarpment, generally marks the northwest border of the Newark Basin, although a belt of gneiss underlies a more subdued upland extending south of this escarpment to the west of Lebanon. Surficial deposits in the Califon quadrangle include glacial, river, and hillslope sediment and weathered-rock material. The surficial deposits occur in a landscape shaped by two major episodes of river incision, a glaciation, and repeated periods of cold climate. Glacial sediments were laid down during a pre-Illinoian glaciation between 800,000 years ago (800 ka) and 2 million years ago (2 Ma). Hillslope and alluvial-fan and some of the river sediments were laid down primarily during the periods of cold climate. Floodplain sediments are primarily of postglacial age. Weathered-rock materials are produced continuously under both cold and temperate climate by mechanical and chemical breakdown of bedrock. The accompanying map and sections show the surface extent and subsurface relations of these deposits. The composition and thickness of the deposits, and the events they record, are described in the Description of Map Units. Well and boring data used to infer the thickness and subsurface distribution of the deposits are provided in table 1 (in pamphlet). Figure 1 shows geomorphic and glacial features in the quadrangle, and figure 2 shows the thickness of surficial deposits and weathered bedrock. The chronologic relationships of the deposits and episodes of erosion are shown in the Correlation of Map Units. The hydrology of the surficial deposits and the history of geomorphic and glacial events in the quadrangle and adjacent areas are briefly described in the two following sections. Bedrock was mapped by Volkert (1989, unpublished). HYDROLOGY OF SURFICIAL DEPOSITS Surficial deposits in the Califon quadrangle are generally too thin or insufficiently permeable to be aquifers, although several domestic wells draw from granular weathered gneiss (unit Qwg, wells 56, 118, 120, and possibly 242, in table 1) and granular materials within weathered carbonate rock (unit Qwcb, wells 33, 34, 37, 145 146, 150, 164, and 166, in table 1), which may include collapsed fluvial sand and gravel, gneiss colluvium, or carbonate-rock gravel. One well (429) draws from weathered carbonate-clast conglomerate, which is cavernous and permeable where the carbonate clasts have decomposed (see comments for wells 353 and 429 in table 1; well 353 was completed below the weathered zone). Hydraulic conductivities of surficial deposits may be estimated from aquifer-test and laboratory data on similar deposits in New Jersey (compiled in Stanford, 2000 and Mennel and Canace, 2002). Clean sand and gravel in fluvial deposits (parts of units Qal, Qaf, Qtl, Qtu, and Qcal) are highly permeable, having estimated hydraulic conductivities that range from 10 1 to 10 3 feet per day (ft/d). Weathered rock, colluvium, glacial sand and gravel, and alluvial deposits with silty sand matrix (parts of Qwg, Qwc, Qcg, Qps, Qal, Qtl, Qtu, Qcal) are also permeable, having estimated hydraulic conductivities from 10 -1 to 10 2 ft/d. Weathered rock, colluvium, terrace deposits, and till with clayey silt, silty clay, and sandy clayey silt matrix (parts of Qwcb, Qwg, Qwb, Qwd, Qws, Qcg, Qcd, Qcs, Qccb, Qcb, Qtl, Qtu, Qtuo, and Qpt) are of low permeability, having hydraulic conductivities of 10 -5 to 10 -3 ft/d. Sandier, less clayey phases of these materials are somewhat more permeable, having estimated hydraulic conductivities of 10 -3 to 10 -1 ft/d. Fill has variable hydraulic conductivity that depends on the clay and silt content of the material. Fill composed of sand, cinders, gravel, demolition debris, slag, and trash, may be highly permeable. GEOMORPHIC AND GLACIAL HISTORY The oldest landscape feature in the quadrangle is the gently rolling upland atop the Highlands around Fairmount and Farmersville, to the west and south of Cokesbury, and to the north of Little Brook (late Miocene land surface on fig. 1). This upland is part of a regional low- relief erosion surface, termed the "Schooley peneplain" by Davis and Wood (1889), and "Kittatinny base level" by Salisbury (1898), that was thought to be the product of fluvial erosion during an extended period of stable base level, and then preserved as upland remnants on resistant rock during later fluvial incision as base level lowered. This view fell into disfavor in the latter half of the twentieth century, in part because it had been widely and, in some cases, uncritically, applied to dissimilar landforms and broad regions. More recently, improved records of past sea level indicate that the stepwise drops in base level needed to produce and incise planation surfaces in coastal areas of low tectonic activity have occurred within the past 30 million years, suggesting that an updated version of the peneplain theory is plausible in these settings (Stanford and others, 2001). Sea-level data, and the age and topographic position of fluvial and marine sediments in the mid-Atlantic region, indicate that the Schooley surface reached its final form in the middle to late Miocene (15-10 million years ago (Ma)) and was isolated on resistant-rock uplands by river incision in the late Miocene and early Pliocene (10-4 Ma) (Stanford and others, 2001). While erosion on moderate to gentle slopes has continuously modified the Schooley surface, it has done so at a rate much slower than that in the valleys, preserving the general form, if not the details, of the surface. Lowering sea level between 10 and 4 Ma led to river incision along belts of carbonate rock in the Highlands, and on shale in the Newark Basin. This incision formed the South Branch of the Raritan River (hereafter referred to simply as the Raritan) and Rockaway Creek valleys, with floors between 300 and 500 feet below the former base level on the Schooley surface. Another period of stable sea level between 4 and 3 Ma halted river incision and led to a period of valley widening, forming a lower erosion surface (early Pleistocene-Pliocene land surface on fig. 1) on carbonate rock in Long Valley and on shale in the Rockaway Creek basin. The pre-Illinoian glacier advanced into this landscape. It covered nearly the entire quadrangle, reaching a terminal position against the north slope of Cushetunk Mountain (M1 on fig. 1). The pre-Illinoian glaciation occurred in the early Pleistocene (2.6 Ma to 800 ka). Some pre-Illinoian glacial sediments in New Jersey (Ridge, 2004), eastern Pennsylvania (Sasowsky, 1994), and central Pennsylvania (Gardner and others, 1994) are magnetically reversed, indicating that they are older than 800 ka. In New Jersey, pollen in pre-Illinoian lake sediment (Harmon, 1968), and in a preglacial fluvial deposit that is weathered and eroded about as much as the pre-Illinoian till (Stanford and others, 2001), indicate a Pliocene or early Pleistocene age. These observations suggest that the pre-Illinoian glaciation here correlates with the earliest continental glaciation in North America in the early Pleistocene, dated in the Missouri River valley to >2 Ma (Roy and others, 2004). Today, remnants of deeply weathered pre- Illinoian till (Qpt) occur on flat uplands on carbonate rock in Long Valley, on flat uplands and gently sloping headwater areas on shale in the Rockaway Creek valley, and in one flat saddle on the Highlands upland between Farmersville and Fairmount. In these settings, the deposits are less susceptible to erosion. Sand and gravel deposited by meltwater from the pre-Illinioan glacier is preserved in three places in the quadrangle: 1) banked against a gneiss and diabase upland on the west side of the headwaters of the South Branch of Rockaway Creek in Lebanon, 2) a small deposit beneath diabase colluvium exposed in a railroad cut at the foot of Cushetunk Mountain south of Pottersville, and 3) banked on the north side of a basalt ridge in the Rockaway Creek valley near McCrea Mills. In each place, the gravel was most likely laid down in small lakes formed between the retreating ice margin and bedrock hills to the west or south (fig. 1). The deposit at Lebanon includes a higher, more westerly part that rises to 420 feet in elevation and may have been laid down in an earlier, higher lake that spilled across a divide at the same elevation west of Round Valley Reservoir (M2 on fig. 1). To the east, the lower part of the Lebanon deposit rises to an elevation of 340 feet and may have been laid down in a later, lower lake that spilled across a divide at the same elevation to the south, now beneath Round Valley Reservoir (M3 on fig. 1). The deposit at the foot of Cushetunk Mountain is at an elevation of 220 feet and may have been laid down in a lake held in by the terminal ice margin against the foot of the mountain, with a spillway along the ice front to the south across a shoulder of the mountain at the same elevation (M1 on fig. 1). The deposit at McCrea Mills rises to an elevation of 300 feet and may have been laid down in a lake that spilled across a divide at about the same elevation south of Bissell (M4 on fig. 1). If this was the case, the gap through the basalt ridge at McCrea Mills was either blocked by the glacier or had not yet been eroded below 300 feet by Rockaway Creek. Sea level lowered again during and after the pre-Illinoian glaciation, leading to a second period of fluvial incision in the early and middle Pleistocene. The Raritan River and Rockaway Creek cut inner valleys to depths of about 100 feet within the older, broader valleys (the inner valleys are outlined in black on fig. 1). Pre-Illinoian glacial deposits were eroded away over most of their original extent, except on flat uplands or in headwater areas that were upstream of the incising streams. Headwater valleys draining the Highlands upland incised along their lower reaches, where they dropped into Long Valley or descended the Highlands Escarpment into the Newark Basin, forming ravines. In the middle (800-125 ka) and late (125-11 ka) Pleistocene, glaciers entered New Jersey at least twice, and advanced to terminal positions about 8 miles north of Califon. They did not advance into the map area. Additional glacial advances are known from deposits in the midwestern United States but did not reach New Jersey. These glacial advances were accompanied by periods of cold, boreal climate. During these cold periods, forest cover was reduced and permafrost developed, impeding soil drainage and thereby waterlogging the surficial material during thaws. Weathered-rock material on hillslopes became unstable and moved downslope to accumulate as aprons of colluvium (Qcg, Qcd, Qcb, Qccb, Qcs). Where the material was transported downslope into steep tributary channels, streams flushed it into main valleys to form alluvial fans (Qaf). Most of the colluvium at the surface is lightly weathered and was deposited during the most recent glacial period, known as the Wisconsinan stage (80-11 ka). Older, weathered colluvium, deposited during earlier glacial stages, occurs in the subsurface in places. Older colluvium containing weathered and decomposed gneiss clasts was observed beneath 5 feet of fresh-clast gneiss colluvium in a gully on Hell Mountain. Older colluvium containing weathered and decomposed basalt clasts was observed beneath 3 to 5 feet of fresh-clast basalt colluvium in several places west of Oldwick. The surface of some colluvial aprons, particularly the diabase colluvium on Cushetunk Mountain, has a lobate or scalloped form in places, with bouldery lobes alternating with finer-textured swales. Locally, on lower parts of the aprons, boulders are concentrated in broad swales that terminate upslope at scarps. These morphologic features suggest deposition of colluvium on or around perennial snowfields during periods of cold climate, followed by groundwater seepage during temperate climate. Lobes and scarps formed around the hollows created when the snowfields melted. Runoff and seepage washed fine sediment from elevated parts of the colluvium into the swales. More voluminous, persistent seepage in larger swales on lower slopes washed out the fine sediment altogether, leaving boulder lags. Some of the additional sediment shed from hillslopes during cold periods was washed into the Raritan River and Rockaway Creek, where it was deposited in floodplains that are today partially preserved in terraces above the modern floodplain (Qtl, Qtu, Qtuo). The lower terraces (Qtl), which have surfaces 5 to 10 feet above the modern floodplain, grade down the Raritan River valley to late Wisconsinan glaciofluvial terraces in the Bound Brook-Somerville area, and are therefore partly of late Wisconsinan age. Upper terraces along the South Branch of Rockaway Creek (Qtu) have surfaces that are 10 to 20 feet above the modern floodplain. They contain weathered gneiss and sandstone pebbles and cobbles. These features are typical of pre-Wisconsinan glaciofluvial deposits elsewhere in the Raritan valley, indicating an age of 150 ka or older. Erosional remnants of an older terrace (Qtuo) along the South Branch of Rockaway Creek, north of Cushetunk Lake, are 10 to 20 feet higher than the upper terrace and also contain decomposed gneiss pebbles and cobbles. This deposit is probably of pre-Illinoian age. It is younger than the pre-Illinoian glaciation because it is within a valley incised about 50 feet below the base of the pre-Illinoian till. By about 15 ka, as climate warmed at the end of the Wisconsinan stage, forest cover returned and hillslopes stabilized. Deposition of colluvium, alluvial fans, and terraces ceased. Streams and groundwater seepage eroded and incised the colluvial aprons, alluvial fans, and terraces in places. Streams cut down 5 to 10 feet into terraces, then eroded laterally to form the modern floodplain (Qal). Groundwater seepage and runoff on uplands and in headwater areas incised and reworked colluvium and weathered-rock material, depositing mixed alluvium and colluvium (Qcal). Floodplain and upland seepage deposition continues today. DESCRIPTION OF MAP UNITS ARTIFICIAL FILL—Artificially emplaced sand, gravel, silt, clay, and rock fragments, and man-made materials including cinders, ash, brick, concrete, wood, slag, asphalt, metal, glass, and trash. Color variable but generally dark brown, gray, or black. In highway and railroad fills, dams, dikes, made land, waste-rock disposal piles, and small trash fills. As much as 20 feet thick. Many small areas of fill are not mapped. ALLUVIUM—Sand, silt, pebble-to-cobble gravel, cobble-to- boulder gravel, minor clay and peat; fine sediment is dark brown, brown, yellowish-brown, gray, reddish-brown (in Newark Basin); moderately to well sorted, stratified. Contains variable amounts of organic matter. Sand and gravel are deposited in active channels. Sand, silt, clay and peat are deposited in back channels, overbank areas, and groundwater seepage areas, chiefly on broad floodplains. Alluvium includes cobble-to-boulder lags from erosion of gneiss colluvium (Qcg) and weathered gneiss (Qwg) where it overlies these units. As much as 15 feet thick. ALLUVIUM AND COLLUVIUM, UNDIVIDED—Interbedded colluvium as in units Qcg and Qcs, and alluvium consisting of dark brown, yellowish-brown, reddish-yellow, and, in the Newark Basin, reddish-brown, silty sand, sandy silt, to clayey silt, with some organic matter and beds and lag veneers of subangular to subrounded cobbles and boulders of gneiss (adjacent to units Qwg and Qcg), shale chips and flagstones (adjacent to unit Qws), and rounded erratic cobbles and boulders of gneiss, quartzite, and chert (adjacent to unit Qpt). As much as 15 feet thick. Lag deposits are dominant in steeper reaches of valleys. Fine sediment, with variable amounts of organic matter, discontinuously overlies and infills lag deposits in gently sloping reaches. In some steep, narrow valleys, lags have moved downvalley to accumulate as bouldery lobes. This movement may have occurred under cold climate. ALLUVIAL FAN DEPOSITS—Pebble-to-cobble gravel, cobble- to-boulder gravel, sand, silt; brown, yellowish-brown, gray; moderately sorted, stratified. As much as 25 feet thick (estimated). LOWER STREAM TERRACE DEPOSITS—Fine-to-medium sand, silt, clayey silt, pebble-to-cobble gravel, minor boulder gravel (fig. 3); reddish-brown, brown, very pale brown, yellowish-brown, light gray; moderately to well sorted, weakly stratified. Gravel consists of gneiss, quartzite, chert, and, in the Rockaway Creek basin, diabase and red and gray shale and sandstone. Gneiss, diabase, and sandstone clasts are unweathered to partially weathered; quartzite and chert are unweathered. As much as 10 feet thick. Form terraces with surfaces 5-10 feet above the modern floodplain in the Rockaway Creek basin and Raritan River valley. In the Rockaway Creek basin, include some clay and silt slopewash sediment from adjacent hillslopes. UPPER STREAM TERRACE DEPOSITS—Silt, fine-to-medium sand, clayey silt, pebble-to-cobble gravel; reddish-brown, reddish-yellow; moderately sorted, nonstratified to weakly stratified. Gravel consists of quartzite, gneiss, quartzite- conglomerate, diabase, and sandstone. Gneiss, diabase, and some sandstone clasts have thick (>0.25 inch) weathered rinds or are completely decomposed. As much as 15 feet thick. Form terraces 10-20 feet above the modern floodplain in the Rockaway Creek basin. UPPER STREAM TERRACE DEPOSITS, OLDER PHASE—Clayey silt, reddish-brown, with few to some pebbles and cobbles of gneiss, quartzite, and chert. Gneiss clasts are deeply weathered to decomposed, some quartzite and chert clasts are stained yellowish-brown. As much as 15 feet thick. Form an eroded terrace 10 to 20 feet above the upper stream terrace in the South Branch of Rockaway Creek valley. PRE-ILLINOIAN TILL—Yellowish-brown to reddish-yellow; rarely reddish-brown, very pale brown, light gray; silty clay to sandy clayey silt with some (5-10% by volume) to many (10- 40%) subrounded to subangular pebbles and cobbles and few (<5%) to some subrounded boulders (fig. 4). Gravel consists of, in approximate order of abundance, gray and white gneiss, gray and brown quartzite and quartzite-conglomerate, dark-gray chert, gray and red mudstone and sandstone, and reddish-brown quartzite-conglomerate. Boulders are chiefly gray gneiss and gray to white quartzite and quartzite-conglomerate. The mudstone, sandstone, and gneiss gravel clasts have thick (>0.5 inch) weathered rinds or are completely decomposed. Quartzite boulders, and a few gneiss boulders, have yellowish-brown to brownish-yellow surface stains. As much as 50 feet thick but generally less than 30 feet thick. Equivalent to the Port Murray Formation, till facies, of Stone and others (2002). PRE-ILLINOIAN SAND AND GRAVEL—Pebble-to-cobble gravel with yellowish-brown to reddish-brown sand to silty sand matrix. Gravel composition and weathering characteristics as in unit Qpt. Weakly stratified to unstratified; original stratification largely destroyed by weathering and cryoturbation. Interbeds of till as in unit Qpt are common in the deposit near McCrea Mills and may be present in the other deposits. As much as 40 feet thick. Equivalent to the Port Murray Formation, stratified facies, of Stone and others (2002). GNEISS COLLUVIUM—Yellowish-brown, reddish-yellow, brown sandy silt, silty sand, sandy clayey silt with some to many subangular gneiss pebbles and cobbles ("blocky colluvium"), in places underlain by or interbedded with thinly layered reddish- yellow to pinkish-white clayey sand and sandy clay with few angular pebbles and cobbles ("layered colluvium"). Long dimensions of clasts typically are aligned parallel to the hillslope (fig. 5). Blocky colluvium is derived from downslope movement of fractured, weathered bedrock; layered colluvium is derived from downslope movement of saprolite. Colluvium may include rare (<0.1%) quartzite and chert erratics from erosion of pre- Illinoian till. Colluvium on moderate-to-gentle slopes includes cobble-to-boulder lags formed by seepage erosion of weathered gneiss. As much as 70 feet thick. BASALT COLLUVIUM—Reddish-yellow, yellowish-brown, brown, reddish-brown clayey silt, silty clay, minor fine-sandy silt with some to many subangular basalt pebbles and cobbles. Long dimensions of clasts typically are aligned parallel to the hillslope. As much as 15 feet thick. DIABASE COLLUVIUM—Yellowish-brown, brown clayey silt, sandy clayey silt, clayey silty sand, with few to many subangular gray diabase pebbles and cobbles and few to many subrounded gray diabase boulders. As much as 40 feet thick. CARBONATE COLLUVIUM—Yellow, very pale brown, light gray silt and clayey silt with some subangular gray carbonate- rock chips and few subangular gray carbonate-rock flagstones and subrounded pebbles and cobbles of weathered gneiss, quartzite, and chert eroded from unit Qpt. Long dimensions of clasts typically are aligned parallel to the hillslope. As much as 10 feet thick. SHALE COLLUVIUM—Reddish-brown, light reddish-brown clayey silt, silty clay, sandy clayey silt with few to some subangular red shale chips and few to some subrounded pebbles and cobbles of gneiss, quartzite, and chert eroded from unit Qpt. Long dimensions of shale chips typically are aligned parallel to the hillslope. As much as 10 feet thick. WEATHERED GNEISS—Yellowish-brown, yellow, very pale brown, reddish-yellow, silty sand, silty clayey sand to sandy clayey silt, locally micaceous, with few to many subangular pebbles and cobbles of gneiss. Includes mixed clast-and-matrix sediment, granular decomposed rock, fractured rock rubble, and saprolite that preserves original rock structure. Clasts range from unweathered to fully decomposed. On gentle to moderate slopes, well records indicate that clast-and-matrix sediment (described by drillers as "overburden", "hardpan", "sandy hardpan", and "clay hardpan"), which is fractured rock mixed with sandy- clayey saprolitic material by colluviation, cryoturbation, and bioturbation, is generally between 5 and 30 feet thick and commonly overlies or grades downward to saprolite (described by drillers as "rotten rock", "sandstone", "rotten granite", and "soft granite") that may be as much as 80 feet thick over unweathered rock. In general, saprolite tends to be somewhat thicker on metasedimentary and metavolcanic gneiss ("gneiss" on fig. 2) than on granitic gneiss ("granite" on fig. 2) because the metasedimentary rocks are more finely layered and foliated, and more micaceous, than the granites, allowing groundwater to penetrate more deeply. On steep slopes, fractured-rock rubble, generally less than 20 feet thick, overlies unweathered bedrock. Total thickness of weathered material is as much as 150 feet but is generally less than 25 feet (fig. 2). The uppermost, clast-and- matrix material may contain traces of quartzite and chert erratic pebbles and cobbles left from erosion of unit Qpt. Unit Qwg includes small areas of weathered quartzite near the contact with carbonate rock (unit Qwcb). Weathered quartzite consists of yellowish-brown to brown silty sand with many angular cobbles and small boulders of brown, gray, and white quartzite and quartzite-conglomerate. Qwgt indicates areas where weathered material is thin or absent and fractured outcrop abundant, typically on the steepest slopes and narrow ridgetops. WEATHERED CARBONATE ROCK—Yellow, very pale brown, reddish-yellow, light gray clayey silt to silty clay, minor sandy silt, with some to many light gray to yellow angular chips and pebbles of carbonate rock. Includes few to some pebbles and cobbles of quartzite, chert, and variably weathered gneiss, and deformed beds and lenses of sand and silty sand, from solution collapse and mixing of overlying glacial, colluvial, and alluvial deposits (units Qpt, Qcg, Qaf). Thickness is highly variable. Greatest thicknesses (100-300 feet) occur along the base of bordering gneiss uplands, where acidic water draining from the uplands infiltrates into carbonate rock from both groundwater seepage and stream loss, and dissolves the rock (fig. 2). Lesser thicknesses (10-40 feet) occur away from the valley walls, where there is less contact with acidic water. Geomorphic evidence for this variation in solution rates includes small solution basins (generally less than 200 feet in diameter) along the base of Fox Hill in Long Valley and along the base of the gneiss upland west of Round Valley Reservoir (solution basins are symboled on map), and a linear topographic low on the west side of Long Valley north of Califon. These features contrast with the higher topography, without solution basins, on carbonate rock away from the base of the gneiss uplands in both places. Qwcbt indicates areas where weathered material is thin or absent and fractured outcrop abundant. WEATHERED SHALE—Reddish-brown, light reddish-brown clayey silt to silty clay with many angular to subangular red (and, in places, gray) shale chips, and a trace to few subrounded pebbles and cobbles of gneiss, quartzite, and chert left from erosion of unit Qpt. Generally less than 5 feet thick. WEATHERED BASALT—Reddish-yellow, reddish-brown, light gray, yellowish-brown, brown clayey silt, silty clay, sandy clayey silt with some to many subangular pebbles and cobbles of basalt. Most clasts have thin (<0.25 inch) clayey-silty reddish-yellow weathering rinds. As much as 15 feet thick. WEATHERED DIABASE—Brown, olive-brown, yellowish-brown sandy clayey silt to clayey sand with some to many angular to subangular gray to brown diabase pebbles, cobbles, and small boulders. As much as 20 feet thick. Qwdt indicates area where weathered diabase is thin or absent and fractured outcrop abundant. WEATHERED CONGLOMERATE—Reddish-brown, reddish- yellow silty sand to clayey silty sand with some to many subangular to subrounded pebbles, cobbles, and boulders of gray carbonate rock and cobbles of purple and gray quartzite and quartzite-conglomerate, and some subangular to subrounded red and gray shale chips and pebbles to cobbles of red siltstone and sandstone. Carbonate clasts are commonly decomposed, producing voids, or clots and lenses of yellow clayey silt residue. May contain traces of gneiss pebbles and cobbles and chert pebbles left from erosion of unit Qpt. As much as 200 feet thick but generally less than 50 feet thick. MAP SYMBOLS Contact--Long-dashed where approximately located, short-dashed where gradational or feather-edged. Some contacts are based on soil mapping by Jablonski (1974). Material observed in hand-auger hole, exposure, or excavation Material formerly observed—Reported in N. J. Geological and Water Survey permanent note collection. Photograph location Excavation perimeter—Line encloses excavated area. Outlines quarries. Bedrock ridge or scarp—Line on crest of ridges or scarps parallel to strike of bedrock. Drawn from stereo aerial photography and LiDAR imagery. Seepage scarp—Line at foot of scarp along which groundwater emerges, water drains downslope from this position. Seepage is also common at the edge of units Qcal and Qal in headwater areas and at the base of steep slopes. Quarry or mine pit--Inactive in 2015. Quarry--Active in 2015. Well reporting thickness of surficial material—Data in table 1. Location accurate within 100 feet. Well reporting thickness of surficial material—Data in table 1. Location accurate within 500 feet. Large or isolated bedrock outcrop--Smaller outcrops also occur within units Qwgt, Qwcbt, and Qwdt but are not mapped separately. Small outcrops along streams or in artificial cuts are also not shown. Refer to Volkert (1989, unpublished) and figure 2 for these outcrop locations. Well on sections--Projected to line of section. Owing to projection, depths of contacts on section may not be identical to those in well. Well number from table 1. Solution basin--Line on rim, pattern in center. Small, shallow basins (maximum depth 5 feet) formed from dissolution of underlying carbonate rock. Drawn from stereo aerial photography and LiDAR imagery. REFERENCES Davis, W. M., and Wood, J. W., 1889, The geographic development of northern New Jersey: Proceedings of the Boston Society of Natural History, v. 24, p. 365-423. Gardner, T. W., Sasowsky, I. D., and Schmidt, V. A., 1994, Reversed polarity glacial sediments and revised glacial chronology, West Branch Susquehanna River, central Pennsylvania: Quaternary Research, v. 42, p. 131-135. Harmon, K. P., 1968, Late Pleistocene forest succession in northern New Jersey: New Brunswick, N. J., Rutgers University, Ph. D. dissertation, 203 p. Jablonski, C. F., 1974, Soil survey of Hunterdon County, New Jersey: U. S. Department of Agriculture, Soil Conservation Service, 131 p. Mennel, W. J., and Canace, Robert, 2002, New Jersey Geological Survey hydro database: N. J. Geological Survey Digital Geodata Series DGS 02-1, www.state.nj.us/dep/njgs/geodata/dgs02-1.zip Ridge, J. C., 2004, The Quaternary glaciation of western New England with correlations to surrounding areas, in Ehlers, J., and Gibbard, P. L., eds., Quaternary glaciations—extent and chronology, part II: Elsevier, p. 169-199. Roy, M., Clark, P. U., Barendregt, R. W., Glasmann, J. R., and Enkin, R. J., 2004, Glacial stratigraphy and paleomagnetism of late Cenozoic deposits of the north-central United States: Geological Society of America Bulletin, v. 116, p. 30-41. Salisbury, R. D., 1898, The physical geography of New Jersey: N. J. Geological Survey Final Report of the State Geologist, v. 4, 200 p. Sasowsky, I. D., 1994, Paleomagnetism of glacial sediments from three locations in eastern Pennsylvania, in Braun, D. D., ed., Late Wisconsinan to pre-Illinoian (G?) glacial and periglacial events in eastern Pennsylvania: Guidebook for the 57 th Friends of the Pleistocene Field Conference, Bloomsburg University, Bloomsburg, Pa., p. 21-23. Stanford, S. D., 2000, Glacial aquifers of New Jersey, in Harper, D. P., and Goldstein, F. R., eds., Glacial geology of New Jersey: field guide and proceedings for the seventeenth annual meeting of the Geological Association of New Jersey: Trenton, N. J., Geological Association of New Jersey, p. IV.1-IV.21. Stanford, S. D., Ashley, G. M., and Brenner, G. J., 2001, Late Cenozoic fluvial stratigraphy of the New Jersey Piedmont: a record of glacioeustasy, planation, and incision on a low-relief passive margin: Journal of Geology, v. 109, p. 265-276. Stone, B. D., Stanford, S. D., and Witte, R. W., 2002, Surficial geologic map of northern New Jersey: U. S. Geological Survey Miscellaneous Investigations Map I-2540-C, scale 1:100,000. Volkert, R. A., 1989, Provisional geologic map of the Proterozoic and Paleozoic rocks of the Califon quadrangle, Hunterdon and Morris counties, New Jersey: N. J. Geological Survey Geologic Map Series GMS 89-3, scale 1:24,000. Volkert, R. A., unpublished, Bedrock geologic map of the Califon quadrangle, Hunterdon and Morris counties, New Jersey: N. J. Geological Survey Open-File Map, dated 2007, scale 1:24,000. On file at the N. J. Geological and Water Survey. Qal Qcal Qaf Qtl Qtu Qtuo Qpt Qps Qcg Qcb Qcd Qccb Qcs Qwg Qwgt Qwcb Qwcbt Qws Qwdt Qwc ! ! ! figure 5 ! 47 . 147 r 47 Qwd Qwb DEPARTMENT OF ENVIRONMENTAL PROTECTION WATER RESOURCES MANAGEMENT NEW JERSEY GEOLOGICAL AND WATER SURVEY SURFICIAL GEOLOGY OF THE CALIFON QUADRANGLE HUNTERDON AND MORRIS COUNTIES, NEW JERSEY OPEN-FILE MAP SERIES OFM 111 pamphlet containing table 1 accompanies map Prepared in cooperation with the U. S. GEOLOGICAL SURVEY NATIONAL GEOLOGIC MAPPING PROGRAM 7000 FEET 1000 1000 0 2000 3000 4000 5000 6000 .5 1 KILOMETER 1 0 SCALE 1:24 000 1/ 2 1 0 1 MILE MAGNETIC NORTH APPROXIMATE MEAN DECLINATION, 1970 TRUE NORTH LOCATION IN NEW JERSEY 11 O CONTOUR INTERVAL 20 FEET NATIONAL GEODETIC VERTICAL DATUM OF 1929 SURFICIAL GEOLOGY OF THE CALIFON QUADRANGLE HUNTERDON AND MORRIS COUNTIES NEW JERSEY by Scott D. Stanford 2016 Figure 3. Pebble, cobble, and boulder gravel in the Lower Stream Terrace Deposits along Rockaway Creek. Note imbrication of pebbles and cobbles as a result of current flow (flow is to the left). Location shown on map and inset. MAP AREA Figure 4. Pre-Illinoian till near Oldwick. Note subrounded shape of cobbles and boulders from glacial transport. Location shown on map and inset. MAP AREA Figure 5. Gneiss colluvium on Hell Mountain. Note angular shape of pebbles and cobbles, and the rough horizontal alignment of long dimensions of cobbles as a result of downslope transport. Location shown on map and inset. MAP AREA